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Geologi Fisik(Batuan Beku)
Oleh :
Irvani
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Referensi :
• Thomson, G. R. and Turk, J. 1991. Modern Physical Geology. SaunderCollege Publishing, USA.
• Lutgens, F. K., Tarbuck, E. J. and Tasa, D. 2012. Essentials of Geology,11th Edition, Pearson Prentice Hall, New Jersey.
• Freeman, T. 2004. Environmental Geology Laboratory. John Wiley & Sons,Inc., USA.
• Monroe, J. S. and Wicander, R. 2009. The Changing Earth: ExploringGeology and Evolution. 5th Edition. Pre-Press PMG, USA.
• Carlson, D. H., Plummer, C. C. and Hammersley, L. 2011. Physical Geology: Earth Revealed. 9th Edition. McGraw-Hill, New York.
• Bates, R.L. and Jackson, J.A., 1987. Glossary Geology. 3th Edition. American Geological Institute Elexandria, Virginia.
• Williams, L. 2004. Earth Science Demystified. McGraw-Hill, New York.
• Frisch, W., Meschede, M. And Blakey, R., 2011. Plate Tectonics :
Continental Drift and Mountain Building. Springer-Verlag Berlin Heidelberg.German.
• DLL
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Materi :
- Pendahuluan (P.1)- Sejarah, Struktur & Komposisi Bumi (P.2)
- Proses-Proses Geologi & Tektonik Lempeng (P.3-4)
- Pengenalan Unsur, Mineral & Batuan (P.5-8) :
- Unsur & Mineral
- Batuan Beku- Batuan Sedimen
- Batuan Metamorf
- Prinsip Stratigrafi, Paleontologi & Umur Geologi (P.9)
- Pengenalan Struktur Geologi (P.10-11)
- Pengenalan Hidrogeologi & Geomorfologi (P.12)- Pengenalan Kebencanaan Geologi (P.13)
- Pengenalan Peta, Kompas, Navigasi dan PeralatanGeologi (P.14)
- Kuliah Lapangan (Situasional)
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THE ROCK CYCLE
Carlson, et al. 2011
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The Rock Cycle - Plate Tectonics (Convergent
Plate Boundary)
Carlson, et al. 2011
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Locations of Magma Formation
(Schmincke, 2004)
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Magma is molten rock, usually rich in silica and
containing dissolved gases. (Lava is magma on the
Earth’s surface.
Country rock, incidentally, is an accepted term for anyolder rock into which an igneous body intruded.
Carlson, et al. 2011
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3 model offormation of
basaltic magmasfrom partialmelting ofperidotite(Schmincke, 2004)
Setijadji (2011) - Slide
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Carlson, et al. 2011
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Carlson, et al. 2011
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Magma Source: Partial Melting
Mineral
Hypothetical Solid Rock:Intermediate Composition
A (Mafic)
B (Int)
C (Felsic)
Melting
Temp
1200°C
1000°C
800°C
Temperature = 500°C
Setijadji (2011) - Slide
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Mineral
A (Mafic)
B (Int)
C (Felsic)
Melting
Temp
1200°C
1000°C
800°C
Temperature = 900°C Magma
Setijadji (2011) - Slide
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Mineral
A (Mafic)
B (Int)
C (Felsic)
Melting
Temp
1200°C
1000°C
800°C
Temperature = 900°C
Magma
Magma Separates Felsic
Remaining Rock: More Mafic
Setijadji (2011) - Slide
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Composition: Magma Source
Mafic Intermediate Felsic
Source: Partial Melting of ultramafic mantle at
Divergent Zones and…
Ultramafic mantle
Setijadji (2011) - Slide
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Mafic Intermediate Felsic
Source: Partial Melting of ultramafic mantle at
Divergent Zones and … Hot Spots
..... Composition: Magma Source
Setijadji (2011) - Slide
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Mafic Intermediate Felsic
Source: Partial Melting of mantle, ocean crust and continent at
Subduction Zones
...... Composition: Magma Source
Setijadji (2011) - Slide
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Mafic Intermediate Felsic
Source: Partial melting felsic continent above
Hot Spots & Subduction Zones
...... Composition: Magma Source
Setijadji (2011) - Slide
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The Origin of Magma at Spreading Ridges
and Subduction Zones
Monroe & Wicander, 2009
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Hot Spot and the Origin of Magma
Monroe & Wicander, 2009
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MAGMATIC DIFFERENTIATION
Lutgens, et al. (2012)
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Assimilation and Magma Mixing
Lutgens, et al. (2012)
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Monroe & Wicander, 2009
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Magma Mixing
Carlson, et al. 2011
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ROCK AND MINERAL TYPES
• Examples of Igneous Rocks and their constituent
minerals :
Basalt, Gabbro, Rhyolite, Granite
• Basalt and Gabbro differ not in composition, but in
crystallinity; likewise Rhyolite and Granite.
• Basalt and Gabbro differ in relative composition, of the
five major constituents above, from Rhyolite and Granite.
• Basalt and Rhyolite have small crystals because they are
erupted by volcanoes and cool rapidly from the moltenstate.
• Gabbro and Granite have large crystals because they
cool slowly from the molten state, underground.Setijadji (2011) - Slide
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Igneous MineralsMineral Properties
Olivine Green to yellow-green; vitreous; fractures;
small, equidimensional grains
Plagioclase Usually white or gray;
2 cleavages at 90°;
elongate grains; striations sometimes visible
Pyroxene Greenish black or brow nish black;rather dull luster;
blocky grains
Amphibole Black with shiny, splinter y appearance;
two cleavages at 60° and 120°;elongate grains
Biotite Shiny, black sheets;
one perfect cleavage
Orthoclase Usually white or pin k;
2 cleavages at 90°;equidimensional grains
Muscovite Shiny, silvery sheets;
one perfect cleavage
Quartz Colorless to gray;vitreous with conchoidal fracture;irregular grains in intrusive rocks;
equidimensional phenocrysts in extrusive rocks
Setijadji (2011) - Slide
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Lutgens, et al. (2012)
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Setijadji (2011) - Slide
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28
Types of Minerals
• Essential – Minerals which must be
present in order for a rock to be classified
with a certain name
• Accessory – Minerals need not bepresent in a rock, but which may be
present in small amounts
Setijadji (2011) - Slide
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Compositional Terms for Igneous Rocks
Felsic: feldspar + silica
~55-70% silica, K-feldspar > 1/3 of feldspars present
light-colored silicate minerals — Continental crust
Intermediate: between felsic and mafic
~55-65% silica, plag > 2/3 of feldspars present
Na-rich plag predominates over Ca-rich plag
Mafic: magnesium + ferric iron
~45-50% silica; Ca-rich plag dominant feldspar
dark silicate minerals — Oceanic crust
Ultramafic: >90% mafic minerals, silica < 45%, few or no
feldspars Mantle-derived
Setijadji (2011) - Slide
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Composition of Igneous Rocks
Monroe & Wicander, 2009
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Best, 2003
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Carlson, et al. 2011
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Textural Classification of Igneous Rocks
Phaneritic: crystals visible with naked eye
Plutonic or intrusive rocks
Aphanitic: crystal too small for naked eye
Volcanic or extrusive rocks
Porphyritic: two different, dominant grain sizes
Large xtals = phenocrysts; small xtals =
groundmassFragmental: composed of disagregated igneous
material Pyroclastic rocksSetijadji (2011) - Slide
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Igneous Rock Textures
Monroe & Wicander, 2009
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35
Porphyritic Size Distribution
• Porphyritic - bimodal size distribution,with large grains surrounded by numeroussmall grains or glass
• Phenocrysts - Large crystals formed byrelatively slow cooling below the earth’ssurface
• Groundmass - Small crystals or glass,formed by more rapid cooling
Setijadji (2011) - Slide
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Textural Classification of Igneous Rocks
Pegmatitic: very large xtals (cm to 10s of cm); i.e., slowlycooled
Forms veins or layers within plutonic body
Glassy: non-crystalline; cools very fast (e.g., obsidian)Volcanic rocks
Vesicular: vesicles (holes, pores, cavities) form as gasesexpand
Volcanic rocks
Setijadji (2011) - Slide
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Igneous Textures - Crystalline
Coarse Grained Fine Grained
Phaneritic Aphanitic
Setijadji (2011) - Slide
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Igneous Textures - Crystalline
Porphyritic
Phenocrysts
Groundmass
Setijadji (2011) - Slide
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Glassy
Vesicular
Igneous Textures - Crystalline
Setijadji (2011) - Slide
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Igneous Textures - Pyroclastic/Fragmental
Made of rock fragments
rather than crystals
Setijadji (2011) - Slide
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Types of Igneous Rocks
GraniteDioriteGabbro
RhyoliteAndesiteBasalt Dacite
GranodioriteMafic Intermediate Felsic
F i n e
C
o a r s e
Setijadji (2011) - Slide
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Ultramafic Rock - Dunite
Setijadji (2011) - Slide
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Schematic block diagram of some intrusive bodies.
Bentuk Tubuh Batuan Beku (intrusif)
Setijadji (2011) - Slide
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Monroe & Wicander, 2009
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Massive Intrusive Bodies:
Batholiths, Stocks, and Laccoliths
BATHOLITHS. By far the largest intrusive igneous bodies
are batholiths(bathos = depth, lithos = stone). Batholiths
occur as mammoth linear structures several hundreds of
kilometers long and up to 100 kilometers wide.
STOCKS. By definition, a plutonic body must have a
surface exposure greater than
100 square kilometers (40 square miles) to be considered
a batholith. Smaller plutons of this type are termed stocks.LACCOLITHS.
Lutgens, et al. (2012)
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Lutgens, et al. (2012)
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Lutgens, et al. (2012)
Batholiths
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Tablular Intrusive Bodies: Dikes and Sills
Lutgens, et al. (2012)
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Lutgens, et al. (2012)
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Lutgens, et al. (2012)
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Carlson, et al. 2011
Xenoliths, fragments of rock that are distinct from the body of igneous
rocks in which they are enclosed.
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Carlson, et al. 2011
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1. Klasifikasi Batuan Piroklastik
(a) Based on type of material. After Pettijohn (1975) Sedimentary Rocks, Harper & Row, and
Schmid (1981) Geology, 9, 40-43. (b) Based on the size of the material. After Fisher (1966)
Earth Sci. Rev., 1, 287-298.Setijadji (2011) - Slide
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U i i k li
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Best, 2003
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2.A. Klasifikasi Batuan Beku
Fanerit yang Baku adalah
Klasi fikasi QAPF dari IUGS
(Streckeisen, 1976)
A classification of the phaneritic igneous rocks. a.
Phaneritic rocks with more than 10% (quartz + feldspar +
feldspathoids). After IUGS.
Syarat:
1.Batuan harus mengandung minimal
total mineral Plagioklas, Ortoklas dan
Kuarsa (atau Feldspatoid) minimal 10%
2.Jumlah mineral-mineral tersebut
dinormalisasi ke 100%
Quartz-richGranitoid
9090
6060
2020 Alkali Fs.Quartz Syenite
QuartzSyenite
QuartzMonzonite
Quartz
Monzodiorite
Syenite Monzonite Monzodiorite
(Foid)-bearingSyenite
5
10 35 65
(Foid)-bearingMonzonite
(Foid)-bearingMonzodiorite
90
Alkali Fs.
Syenite
(Foid)-bearing Alkali Fs. Syenite
10
(Foid)Monzosyenite
( F o i d ) S
y e n i t e
(Foid)Monzodiorite
( F o i d ) G
a b b r o
Qtz. Diorite/Qtz. Gabbro
5
10
Diorite/Gabbro/ Anorthosite
(Foid)-bearingDiorite/Gabbro
60
(Foid)olites
Quartzolite
Granite Grano-diorite
T o n a l i t e
A l k
a l i F
e l d s p a r G
r a n i t e
Q
A P
F
60
2. Klasifikasi Batuan Plutonik
Setijadji (2011) - Slide
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Best, 2003
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A classification of the phaneritic igneous rocks.
b. Gabbroic rocks. c. Ultramafic rocks. AfterIUGS.
Plagioclase
OlivinePyroxene
G a b b r o
T r o
c t o
l i t e Olivine gabbro
Plagioclase-bearing ultramafic rocks
90
(b)
Anorthosite
OlivineOlivine
ClinopyroxeneClinopyroxeneOrthopyroxeneOrthopyroxene
LherzoliteLherzolite
H a r z b
u r g i t
e
W e h
r l i t e
Websterite
OrthopyroxeniteOrthopyroxenite
ClinopyroxeniteClinopyroxenite
Olivine Websterite
PeridotitesPeridotites
PyroxenitesPyroxenites
90
40
10
10
DuniteDunite
(c)
Batuan Mafik
(Gabbroit)
Batuan Ultramafik
2. B. Klasifikasi IUGS untuk Batuan Beku Fanerit
yang Mafik (b) dan Ultramafik (c)
Setijadji (2011) - Slide
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A classification and nomenclature of volcanic
rocks. After IUGS.
(foid)-bearing Trachyte
(foid)-bearing Latite
(foid)-bearing Andesite/Basalt
(Foid)ites
10
60 60
35 65
10
20 20
6060
F
A P
Q
Rhyolite Dacite
Trachyte Latite Andesite/Basalt
Phonolite Tephrite
3. Klasifikasi Batuan Beku Afanit (Vulkanik) yang Bakuadalah dari IUGS (Streckeisen,1976)
Syarat:
1.Batuan harus mengandung minimal
total mineral Plagioklas, Ortoklas dan
Kuarsa (atau Feldspatoid) minimal
10%2.Jumlah mineral-mineral tersebut
dinormalisasi ke 100%
Setijadji (2011) - Slide
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Klasifikasi Batuan Vulkanik
• Secara umum, penamaan batuanvulkanik non-piroklastik adalahberdasarkan komposisi mineral penyusunnya, dengan menggunakanklasifikasi QAPF yang disusunoleh Streckeisen (1967).
• Namun, jika prosentasi modal mineral yang disyaratkan untukklasifikasi tersebut tidak dipenuhi, maka klasifikasi tersebuttidak bisadigunakan. Kandungan mineral sering tidak bisa ditentukan secara
prosentase modal karena kehadiranmineral berukuran halus ataukarena kehadiranmaterial gelasan.
• Untuk mengatasi hal tersebut , maka IUGS Subcommission on theSystematics of Igneous Rocks membuat rekomendasi untukmembuatberdasarkan diagram Total Alkali – Silika atau dikenal sebagai diagram TAS (Le Bass dkk., 1986).
• Klasifikasi ini dipakai jika 1) analisa kimia yang valid diperoleh, 2)analisis modal mineral tidak diperoleh dan 3) tidak berlaku untuk batuanvulkanik piroklastik.
Setijadji (2011) - Slide
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3.B. Klasifikasi TAS (Total Alkali Silica) untuk
Batuan Vulkanik
A chemical classification of volcanics based on total alkalis vs. silica. After Le Baset al. (1986) J.
Petrol., 27, 745-750. Oxford University Press. Setijadji (2011) - Slide
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COMPOSITION (Minerals Present)
Ultramafic
Olivine(Pyroxene)
Mafic
Ca-Plagioclase
Pyroxene
Olivine
Intermediate
Na-Plagioclase
Amphibole
Pyroxene
Biotite
Intermediate
Na-PlagioclaseAmphibole
Quartz
Biotite
Felsic
QuartzOrthoclase
Biotite
Na-Plagioclase
Coarse-
grained*
DUNITE GABBRO DIORITE GRANODIORITE GRANITE
Fine-
grained*BASALT ANDESITE DACITE RHYOLITE
Glassy OBSIDIAN
Vesicular SCORIA PUMICE T E X T U R E S
Fragmental
(Pyroclastic)TUFF
*Some igneous rocks have a porphyritic texture. If a rock has 2 grain sizes, the rock is named after
the smaller grain size and the word porphyritic is added as an adjective.For example, if a rock is
predominantly fine-grained and mafic, it would be a basalt. If phenocrysts are present in the fine-
grained matrix, this rock would be called a porphyritic basalt.
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Lutgens, et al. (2012)
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Lutgens, et al. (2012)
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Terima Kasih
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